Translator Disclaimer
1 February 2008 A Glacier Inventory for the Buordakh Massif, Cherskiy Range, Northeast Siberia, and Evidence for Recent Glacier Recession
Author Affiliations +

The Buordakh Massif, in the Cherskiy Range of northeast Siberia, contains mountains over 3000 m and, despite its arid climate, numerous glaciers. This paper presents a glacier inventory for the region and documents some 80 glaciers, which range in size from 0.1 to 10.4 km2 (total glacierized area is ca. 70 km2). The inventory is based on mapping derived from Landsat 7 ETM satellite imagery from August 2001, augmented with data from field investigations obtained at that time. The glaciers in this region are of the ‘firn-less,’ cold, continental type, and their mass balance relies heavily on the formation of superimposed ice. The most recent glacier maximum extents have also been delineated, and these are believed to date from the Little Ice Age (ca. A.D. 1550–1850). Glacier areal extent has reduced by some 14.8 km2 (ca. 17%) since this most recent maximum. Of the 80 glaciers catalogued, 49 have undergone a measurable retreat from their most recent maximum extent.


Retreat of mountain glaciers affects regional freshwater resources and will contribute to sea-level rise over the next 50 to 150 years (e.g. Arendt et al., 2002; Raper and Braithwaite, 2006). Glacier retreat is widespread (e.g. Oerlemans, 1994, 2005) but the magnitude and spatial pattern of this retreat is uncertain (Braithwaite, 2002; Kargel et al., 2005). There are some regions where glacier attributes are unknown and for which glacier inventories have not yet been compiled.

The Buordakh Massif, in the Cherskiy Range of northeast Siberia is one of those regions which has been lacking a glacier inventory. This mountain range was first documented following an expedition led by Obruchev in 1926, but Nekrasov and Sheinkman (1981) were the first to publish a report about the glaciers in this region, although the maps accompanying this work were generalized and without a scale. Their work was based upon aerial photographs obtained in 1970 and supplemented with field investigations conducted between 1971 and 1976 by the Institute for Permafrost Research of the Russian Academy of Science. The data from these field investigations include glacier geometries, geomorphological context, measurements of the vertical distribution of ice temperature and accumulation, and ablation rates (limited to 1971 and 1972). Ice flow velocities were also measured on Obruchev and Sumgin glaciers in 1972 (Nekrasov et al., 1973). These investigations represented all the scientific work conducted in the region until 2001 when fieldwork was conducted by two of the present authors within the framework of a joint Russian/British expedition.

The aims of this paper are (1) to describe the glaciers of the Buordakh Massif based on remotely sensed imagery and field surveys, and (2) to produce a satellite-based glacier inventory for the region.

Study Area

Multiple glaciations have affected the Cherskiy Range during the Quaternary. Alpine glaciers descended to between 1500 and 1300 m a.s.l. during the Middle Pleistocene (Arkhipov et al., 1986). In the Late Pleistocene the glaciation was possibly more extensive, occupying some 40% of northeast Siberia, and it has been presumed that all interior mountains over 2000 m had ice cover (Arkhipov et al., 1986). During the Last Glacial Maximum the main center of ice was located west of the Cherskiy Range in the Verkhoyansk Range, and ice extended out into the lowlands in the form of a piedmont glacier. In the Cherskiy Range ice was generally restricted to the higher areas where cirque and valley glaciers formed (Chanysheva and Bredikhin, 1981). By the time of the post-glacial climatic optimum (7 to 5 ka BP) it is thought likely that all glaciers had disappeared (Bespalyy, 1984) and, therefore, the contemporary glaciers postdate this period. Presently, the main concentration of glaciers in the Buordakh Massif, Cherskiy Range, are centered around 65°12′N, 145°56′E.

East of the central Yakutian Plain, the geology of Siberia is complex and arises from continental collision and accretion in the Mesozoic (Molnar and Tapponier, 1975). This vast area consists of the Verkhoyansk and Cherskiy mountain ranges, which are separated by the Lena, Yana, Indigirka, Kolyma, and Anadyr Rivers and their tributaries (Huh et al., 1998). The Cherskiy Range trends NW–SE and contains 3000 m peaks, the highest of which is Mount Pobeda (3147 m).

The climate of the Cherskiy Range is continental and characterized by large seasonal variations in air temperature, atmospheric pressure, and precipitation (Lydolph, 1977; Shahgedanova et al., 2002). Temperatures in winter reach −71 °C and in summer exceed 30 °C. Annual precipitation is 208 mm at the closest meteorological site of Oimyakon. The dominant climatic control in the region is the ‘Siberian high,’ an extensive semi-permanent anticyclone which develops between October and March in response to continuous and strong radiative cooling over the snow-covered surface of northern Asia (Lydolph, 1977; Panagiotopoulos et al., 2005). Being mainly thermally induced, the Siberian high is a shallow cold-core system confined to the lower troposphere. It is replaced by a trough of low pressure above the 700 hPa pressure surface. As a result, the October–March period is characterized by (1) low precipitation below 2000 m a.s.l., which accounts for about 15% of the annual total; and (2) an increase in air temperatures up to 1000 m a.s.l.. Both observations and modeled data suggest that a substantial warming has been observed in eastern Siberia since 1979, both in winter and summer; the former coincides with a pronounced weakening of the Siberian high which has been unprecedented since 1871 (Panagiotopoulos et al., 2005). Furthermore, the recently observed warming and associated changes in atmospheric pressure in northern and eastern Siberia have been extensive (Johannessen et al., 2004; Panagiotopoulos et al., 2005), and a wintertime decline in sea-level pressure in this region has been the highest in the northern hemisphere (Gillet et al., 2003). Climate projections indicate that these trends will likely continue (IPCC, 2001).

Contemporary glaciers in the Buordakh Massif of the Cherskiy Range are of the cold, continental type and belong to the class of ‘superimposed ice’ of Müller (1962) or the ‘infiltration-congelation’ class of Shumskii (1964). The lack of firn and the creation of superimposed ice through the refreezing of percolating meltwater in summer are characteristic (Nekrasov and Sheinkman, 1981). The thin snow cover and very low air temperatures in winter result in low ice temperatures similar to those observed in the neighboring Suntar-Khayata Range, where mean annual temperatures for the near-surface ice have been reported at −10 °C and below (Koreisha, 1963).


Satellite Remote Sensing

Mapping for the area which could be obtained prior to the fieldwork was extremely limited. The available 1:300,000 maps do not show all of the glaciers, and the sketch maps of Nekrasov and Sheinkman (1981) illustrate most of the glaciers but are without a scale and hence were of limited use. In order to conduct the mapping, therefore, two Landsat 7 ETM+ scenes (from 7 August 2000 and 25 July 2001) were obtained. These were purchased in a geocoded format, since the necessary data for geocoding and orthorectification was not available to the authors; specifically, there is no sufficiently detailed Digital Elevation Model available for the area.

Image processing of the August 2000 scene was conducted in order to produce the best possible images for use during the fieldwork. A ‘resolution merge’ image of the study area was created which combined the multi-spectral information from three bands (Bands 7 [2.09–2.35 µm], 5 [1.55–1.75 µm], and 3 [0.63–0.69 µm]) with 30 m ground resolution with the 15 m ground resolution band (Band 8 [0.52–0.90 µm]). This process creates an excellent product for identifying geomorphological features, such as glacier margins. Further image processing enabled the removal of areas obscured by cloud on the image so that it would not be confused with snow. The thermal band (Band 6 [10.4–12.5 µm]) was utilized to differentiate cloud from snow cover (the tops of clouds being much colder than snow on the ground), and this technique proved highly effective. During the initial field period the accuracy of the imagery geocoding was assessed using Ground Control Points (GCPs), whereby specific locations which could be clearly resolved on the imagery were visited on the ground to obtain a reference (in degrees, minutes, and decimal seconds) through the use of a Garmin GPS (Global Positioning System) receiver. These references were then compared to the location report provided by the ‘Inquire Cursor’ function in the Erdas Imagine image-processing software. This process revealed that, in the area under direct investigation at least, the geocoding was accurate to within 1 or 2 pixels of Band 8 (±20 m).

Following the fieldwork, the glacier mapping was conducted from the 25 July 2001 scene (the satellite overpass took place during the fieldwork). Once again image processing enabled a ‘resolution merge’ image to be created and clouds to be accurately identified, although it should be noted that the 2001 imagery had very little cloud cover and that present did not hinder the mapping process. Field data obtained at the GCPs (mentioned above) was also used to validate the image interpretation and ground-based photographs from known locations were also employed. The contemporary glaciers and their most recent limits were delimited (mapped) manually through the creation of vector file overlays on top of the ETM+ imagery using Erdas Imagine software. Attempts to use a classification scheme for the mapping (supervised or unsupervised) proved unsatisfactory. The authors' experience of using Landsat ETM+ scenes for glacier mapping elsewhere (Gurney and White, 2005; Stokes et al., 2006) as well as that of others (e.g. Paul et al., 2002; Heiskanen et al., 2002) informed the whole procedure. The discrimination between areas occupied by ice at the most recent glacier maxima and those outside this limit is greatest in Band 5 of the Landsat ETM+ imagery as is evidenced in Figure 1. Figure 2 further illustrates this point by presenting the difference in pixel Digital Numbers (DNs) for equal-sized populations inside and outside the most recent glacier maximum (cf. Eckardt and Milton, 1999). It was precisely this degree of discrimination which permitted the recently glaciated areas to be readily determined and mapped for the inventory.

Figure 1

Frequency distributions for pixel DN values (Landsat ETM+ Band 5) from inside and outside the most recent glacier maximum for Tsaregradskiy (a) and Obruchev/Sumgin (b).


Figure 2

Average pixel spectra for areas inside and outside the most recent glacier maximum for Tsaregradskiy (a) and Obruchev/Sumgin (b), indicating the power of discrimination in Landsat ETM+ Bands 5 and 7.


Field Observations and Measurements

While in the field eight glaciers were visited and more detailed studies were made of five of these, namely: Tsaregradskiy, Obruchev, Sumgin, Melnikov, and a glacier without a name which is numbered ‘48’ in the inventory. Ground data was collected at over 50 sites in order to verify interpretations of the satellite imagery as previously mentioned. At each site an accurate location (±7 m in the x and y) was obtained using a hand-held Garmin GPS receiver. Ground data collection sites included moraine junctions, inactive moraines, glacial trim-lines and glacier margins associated with the five glaciers mentioned above, and other features that could be used to provide geomorphological context.


A Glacier Inventory for The Buordakh Massif

The glacier inventory given in Table 1 contains information on 80 glaciers in the core area of the Buordakh Massif (some 1550 km2). The inventory does not, however, include those ice aprons, glacierets, and very steep cliff or niche glaciers which occur in the higher parts of the mountain basins above 2000 m. Glacier length ranges from a few hundred meters to over 7 km. Areal extents vary from 0.1 to 10.4 km2, while total glacierized area is believed to be approximately 70 km2. The glaciers which have been mapped are predominantly cirque and small valley glaciers and occur in most valleys above 1650 m. The larger glaciers terminate at elevations of around 1550 m. Maps of the glaciers in the inventory are given in Figures 3 and 4, and Table 1 provides data on the individual glaciers. It should be noted that many of these glaciers have no name and thus the current study has used the numbers previously assigned by Nekrasov and Sheinkman (1981). Since this earlier work covered a larger area, the glacier numbers of the present inventory are not entirely sequential.

Table 1

Glacier inventory for the Buordakh Massif, Cherskiy Range, Siberia. Glacier locations (by number) as can be seen in Figure 4.


Figure 3

The study area (inset) and the contemporary glaciers mapped within it. The Landsat ETM+ imagery for July 2001 used for the mapping provides topographic context.


Figure 4

The glaciers mapped with their number as used in the inventory (see Table 1). The areas in red show the most recent glacier maximum believed to date to the Little Ice Age (see text for discussion).


The four largest glaciers in the region are Tsaregradskiy (41), Obruchev (47), Sumgin (46), and Melnikov (45). These have multiple-cirque origins, and the cirque backwalls are covered with hanging ice nearly up to the ridge-crests. These glaciers have much supraglacial debris which supply moraines on the glacier snouts and which, in turn, have led to the deposition of moraines in the proglacial area. In addition to the largest glaciers there are numerous cirque glaciers and very steep niche or cliff glaciers. Due to the paucity of precipitation, no mountain ice cap has developed (Serebryanny and Solomina, 1996; Solomina, 1999).

In general, the five glaciers that were studied in detail were characterized by debris-covered snouts, large medial moraines, well developed supraglacial streams (some flowing in deeply incised channels), narrow crevasses (at least in summer), extensive ‘dead ice’ in the immediate glacier foreland, and well defined trim-lines above the current glacier surface in their lowermost parts. The surface of Sumgin glacier displayed numerous slush pools (also referred to as ‘snow swamps’, e.g. Hambrey and Alean, 2004) which, in turn, generated slush flows.


Glacier Retreat Since The Most Recent Maximum

It is believed that most glaciers in the study area achieved their maximum Holocene extents during the Little Ice Age (LIA, ca. A.D. 1550–1850; see Matthews and Briffa, 2005; Solomina, 2000). The moraines are unvegetated and only small lichens have colonized boulders in the glacier forelands. Lichen thalli diameters obtained from the foreland of Melnikov Glacier by the present authors yielded an average size of 15.5 mm inside the most recent glacial limit compared with 86.1 mm just outside the glacial limit. The lack of absolute dating or a locally derived lichen growth curve, however, prevents more precise age estimates of the moraines of this study. Nevertheless, we suggest that the most recent glacier maximum discussed in this paper relates to the LIA.

The glaciers lost about 14.8 km2 between the end of the LIA and 2001, which represents a reduction in glaciated area of 17%, corresponding to a mean annual rate of just 0.11%. The magnitude of loss is not uniform throughout the Buordakh Massif; with 62% of the glaciers displaying a measurable retreat from their most recent maximum extent and 38% appearing to be stable, although a proportion of these may, of course, have lost mass through thinning. The pattern and extent of the retreat is illustrated in Figure 5.

Figure 5

Data on the amount of retreat since the most recent maximum.


Recession rates in the Buordakh Massif appear to be lower than those reported for other mountainous areas of northeastern Siberia. For example, in the Suntar-Khayata glacier termini have retreated by 0–19% and 5–28% between the end of the LIA and 1973 in the northern and southern sectors of the mountains, respectively (Ananicheva et al., 2005). Most of the retreat (70–80%) occurred between the LIA and 1945 while the period between 1945 and 1973, characterized by low summer temperatures (Johannessen et al., 2004), accounts for the remaining loss of ice.


Using Landsat ETM+ imagery, we have compiled the first georeferenced glacier inventory for the Buordakh Massif, Cherskiy Range, northeast Siberia. Eighty glaciers were mapped and combined account for ca. 70 km2. The glaciers are predominantly cirque and small valley glaciers of the alpine type and occur in most valleys above 1650 m. The extreme continental climate of the Cherskiy Range, with very low winter temperatures and precipitation and relatively high summer temperatures, results in cold glaciers without firn where superimposed ice formation is important.

Although the date of the most recent glacial maximum is poorly constrained, it is likely that it relates to the Little Ice Age maximum (cf. Solomina, 2000). Our analysis suggests that the areal extent of the glaciers in the Buordakh Massif has reduced by around 17% since this time. This reduction is somewhat lower than that reported for other mountainous areas in NE Siberia (e.g. Ananicheva et al., 2005).


The Siberian fieldwork was part of a Russian/British expedition mounted in July/August 2001 by the Russian Ministry for Emergencies (EMERCOM) and the Royal Logistic Corps of the British Army. Individuals within these groups warranting specific mention include Fraser Coleman, Vladimir Donin, Chris Emerton, Phil Kirby, Andrey Legoshin (Russian Leader), Vladimir Legoshin, Tim Mayers, Sam Pambakian, Ned Rimmer, Tim Smith (British Leader), Graeme Stanbridge, and John Starling. Anastassia Rozova contributed to the field investigations. Funding was obtained from the Ministry of Defence and the Foreign and Commonwealth Office (U.K.) and EMERCOM (Russia), and the expedition received the WEXAS International Award from the Expedition Research Grants Programme of the Royal Geographical Society (with Institute of British Geographers). Comments provided by the editors and two anonymous referees have proved invaluable.

References Cited

  1. M. D. Ananicheva, M. M. Koreisha, and S. Takahashi . 2005. Assessment of glacier shrinkage from the maximum in the Little Ice Age in the Suntar Khayata Range, north-east Siberia. Bulletin of Glaciological Research 22:9–17. Google Scholar

  2. A. A. Arendt, K. E. Echelmeyer, W. D. Harrison, C. S. Lingle, and V. B. Valentine . 2002. Rapid wastage of Alaska glaciers and their contribution to rising sea level. Science 297:382–386. Google Scholar

  3. S. A. Arkhipov, L. L. Isayeva, V. G. Bespalyy, and O. Glushkova . 1986. Glaciation of Siberia and north-east USSR. Quaternary Science Reviews 5:463–474. Google Scholar

  4. V. G. Bespalyy 1984. Late Pleistocene mountain glaciation in northeastern USSR. In A. A. Velichko, H. E. Wright, and C. W. Barnosky , editors. Late Quaternary environments of the Soviet Union London Longman. 31–33. Google Scholar

  5. R. J. Braithwaite 2002. Glacier mass balance: the first 50 years of international monitoring. Progress in Physical Geography 26:76–95. Google Scholar

  6. M. N. Chanysheva and A. V. Bredikhin . 1981. O granites pleistotsenovyh oledededii v basseine reki Kolymy [On the extent of the Pleistocene glaciations in the River Kolyma Basin]. Geomorfologiya [Geomorphology] 3:97–103. [In Russian]. Google Scholar

  7. F. D. Eckardt and E. J. Milton . 1999. The relationship between time since deglaciation and the reflectance of glacial forelands. Remote Sensing of Environment 67:244–247. Google Scholar

  8. N. P. Gillet, F. W. Zweirs, A. J. Weaver, and P. A. Stott . 2003. Detection of human influence on sea-level pressure. Nature 422:292–294. Google Scholar

  9. S. D. Gurney and K. White . 2005. Sediment magnetic properties of glacial till deposited since the Little Ice Age maximum for selected glaciers at Svartisen and Okstindan, northern Norway. Boreas 34:75–83. Google Scholar

  10. M. Hambrey and J. Alean . 2004. Glaciers Cambridge Cambridge University Press. 394. Google Scholar

  11. J. Heiskanen, K. Kajuutti, M. Jackson, H. Elvehœy, and P. Pellikka . 2002. Assessment of glaciological parameters using Landsat satellite data in Svartisen, northern Norway. EARSeL Proceedings 2:34–42. Google Scholar

  12. Y. Huh, G. Panteleyev, D. Babich, A. Zaitsev, and J. M. Edmond . 1998. The fluvial geochemistry of the rivers of eastern Siberia: II. Tributaries of the Lena, Omoloy, Yana, Indigirka, Kolyma and Anadyr draining the collisional/accretionary zone of the Verkhoyansk and Cherskiy Ranges. Geochimica et Cosmochimica Acta 62:2053–2075. Google Scholar

  13. IPCC J. T. Houghton, Y. Ding, D. G. Griggs, M. Noguer, P. J. Vander Linden, X. Dai, K. Maskell, and C. A. Johnson , editors. 2001. Climate change 2001: The scientific basis. Contribution of Working Group 1 to the Third Assessment Report of the Intergovernmental Panel on Climate Change Cambridge Cambridge University Press. 944. Google Scholar

  14. O. M. Johannessen, L. Bengtsson, M. W. Miles, S. I. Kuzmina, V. A. Semenov, G. V. Alekseev, A. P. Nagurnyi, V. F. Zakharov, L. P. Bobylev, L. H. Pettersson, K. Hasselmann, and H. P. Cattle . 2004. Arctic climate change: observed and modeled temperature and sea ice variability. Tellus 56A:328–341. Google Scholar

  15. J. Kargel, M. J. Abrams, M. P. Bishop, A. Bush, G. Hamilton, H. Jiskoot, A. Kaab, H. Kieffer, E. M. Lee, F. Paul, F. Rau, B. Raup, J. F. Shroder, D. Soltesz, D. Stainforth, L. Stearns, and R. Wessels . 2005. Multispectral imaging contributions to global land ice measurements from space. Remote Sensing of the Environment 99:187–219. Google Scholar

  16. M. M. Koreisha 1963. Sovremennoe oledeneniye khrebta Suntar-Khayata [Present glaciation of the Suntar-Khayata Range]. In. Rezultaty issledovaniy po programme MGG. Glyatsiologiya [Research results of the IGY programme. Glaciology]. 11 Moscow AN SSSR. 170. [in Russian]. Google Scholar

  17. P. E. Lydolph 1977. Climates of the Soviet Union AmsterdamOxford Elsevier. 443. Google Scholar

  18. J. A. Matthews and K. R. Briffa . 2005. The ‘Little Ice Age’: re-evaluation of an evolving concept. Geografiska Annaler 87A:17–36. Google Scholar

  19. P. Molnar and P. Tapponier . 1975. Cenozoic tectonics of Asia: effects of a continental collision. Science 189:419–426. Google Scholar

  20. F. Müller 1962. Zonation in the accumulation area of the glaciers of Axel Heiberg Island, NWT, Canada. Journal of Glaciology 4:302–311. Google Scholar

  21. I. A. Nekrasov and V. S. Sheinkman . 1981. Katalog lednikov SSSR [Glacier catalogue of the USSR], 17 (7, parts 2, 4), 19 (part 4) Leningrad Gidrometeoizdat. 88. [in Russian]. Google Scholar

  22. I. A. Nekrasov, I. V. Klimovskiy, and V. S. Sheinkman . 1973. Glyatsiologicheskiye issledovaniya v khr.Ulakhan-Chistayskiy (gornaya sistema Cherskovo) [Glaciological investigations in Ulakhan-Chistay Range, Cherskiy Mountains]. Materialy glyatsiologicheskikh Issledovaniy [Data of glaciological studies] 22:174–180. [in Russian]. Google Scholar

  23. J. Oerlemans 1994. Quantifying global warming from the retreat of glaciers. Science 264:243–245. Google Scholar

  24. J. Oerlemans 2005. Extracting a climate signal from 169 glacier records. Science 308:675–677. Google Scholar

  25. F. Panagiotopoulos, M. Shahgedanova, A. Hannachi, and D. B. Stephenson . 2005. Trends and teleconnections of the Siberian high: a rapidly declining centre of action. Journal of Climate 18:1411–1422. Google Scholar

  26. F. Paul, C. Huggel, A. Kääb, T. Kellenberger, and M. Maisch . 2002. Comparison of TM-derived glacier areas with higher resolution data sets. EARSeL Proceedings 2:15–21. Google Scholar

  27. S. C. Raper and R. J. Braithwaite . 2006. Low sea level rise projections from mountain glaciers and icecaps under global warming. Nature 439:311–313. Google Scholar

  28. L. R. Serebryanny and O. N. Solomina . 1996. Glaciers and climate of the mountains of the former USSR during the Neoglacial. Mountain Research and Development 16:157–166. Google Scholar

  29. M. Shahgedanova, V. Perov, and Y. Mudrov . 2002. The mountains of northern Russia. In M. Shahgedanova , editor. The physical geography of northern Eurasia Oxford Oxford University Press. 284–313. Google Scholar

  30. P. A. Shumskii 1964. Principles of structural glaciology New York Dover Publications. 497. Google Scholar

  31. O. N. Solomina 1999. Gornoe oledneie Evrazii v golotsene [Montane glaciation in northern Eurasia in the Holocene] Moscow Nauchny Mir Publishers. 263. [In Russian]. Google Scholar

  32. O. N. Solomina 2000. Retreat of mountain glaciers of northern Eurasia since the Little Ice Age maximum. Annals of Glaciology 31:26–30. Google Scholar

  33. C. R. Stokes, S. D. Gurney, M. V. Shahgedanova, and V. V. Popovnin . 2006. Late-20th-century changes in glacier extent in the Caucasus Mountains, Russia. Journal of Glaciology 52:99–109. Google Scholar

S. D. Gurney, V. V. Popovnin, M. Shahgedanova, and C. R. Stokes "A Glacier Inventory for the Buordakh Massif, Cherskiy Range, Northeast Siberia, and Evidence for Recent Glacier Recession," Arctic, Antarctic, and Alpine Research 40(1), (1 February 2008).[GURNEY]2.0.CO;2
Accepted: 1 April 2007; Published: 1 February 2008

Back to Top